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• early 1983 and seemed to be following a similar pai:tern after recharge in the Spring of 1983. Water levels in well P1 have stayed high since 1984 because the base flow of Pyeatt Creek has increased and has maintained the high levels in the alluvium. Water levels in the Lewis Shale (well P3), which is in contact with the Pyeatt alluvium, have varied very similar to the alluvial aquifer in this area. Water levels in the Second White Sandstone aquifer near. well P5 have been generally increasing, but have shown a yearly cycle of rapidly rising during the Spring and then gradually declining tl'ne remainder of the year. Water levels in the Third White Sandstone well, P8, rose significantly in 1984 and have stayed high except i°or one measurement. The increased heads in the Third White Sandstone acquifer are probably due to large amounts of recharge. Water levels of Johnson Gulch alluvial well, ;J1, are presented in Figure A-23. This plot shows a very slight rise in the water level with time in this alluvial aquifer. The Flume alluvial aquifer is monitored with alluvial wells GC3 and Coy. The water level' in alluvial well, Coy, (see Figure A-24) has risen steadily until January of 1986, except for one outlier level. Water levels at the alluvial aquifer near well Coy have risen much more thane the rise observed upgradient at alluvial well GC3. . 2.2 WATER-LEVEL ELEVATION Three piezometric maps of the Trapper Mine were developed to show the water level flow patterns for the QR, HI and Tlnird White Sandstone aquifers. Water levels from the Fall of 1985 were used in the development of these maps. Map No. 2-1 presents the water-level elevations for the QR aquifer. The GP wells that are shown on this map are the new wells installed for the east area and baseline data for these wells is presently being collected. The water-level elevation is shown by the QR wells, GA1, GD2, GE1, GZ3, and GF6. The ground- water flow in the QR aquifer is mainly to the north. Mining has affected the QR aquifer only close to the D and E pits by causing drawdowns very near the pit edges. Some rise of the contour elevations north of these pits could have occurred by the movement of additional water into the QR aquifers in these areas. Map No. 2-2 presents the water-level elevation contours for the BI aquifer for the Fall of 1985. Wells GB5, GC1, GE2, and GF4 were used in the development of this map. Flow in the HI aquifer has been changed mainly at the A, D and E pits. The overall flow regime in this aquifer is close to its pre-mine conditions. 2-4